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Earth Science Frontiers, Vol. 17, Special Issue, Aug. 2010 ISSN 1005-2321 and Portlandian deposits (Schudack, 1989). This genus is also occurred in Morrison Formation in northern America. The age of this assemblage is considered to be as early as Kimmeridgian and as late as early Berriasian in age. 4. Luanpingella–Eoparacypris–Rhinocypris As- semblage This assemblage is found from the Dabeigou Formation of northern Hebei province and Ershierzan Formation of northern Daxinganling area. The domi- nant forms are Luanpingella and Eoparacypris. They are distinctive in big size and smooth of surface of valves. Eoparacypris was firstly occurred in the Lower Purbeck bed of UK; Rhinocypris is a small ostracoda characterized by the spines ornament. It is ranging from Lower Jurassic to Lower Cretaceous and widely distributed in Europe and Asia; Luanpingella is a endemic genus with limited distribution. This assemblage doesn’t have Cypridea that was flourished in Cretaceous, so its age is later than Cypridea dunkeri zone of the Purbeck bed (Anderson, 1973, 1985; Horne, 1995) and may be Tithonian of Late Jurassic. 5. Minheella–Jinguella–Pinnocypridea Assem- blage The assemblage was found in Kapushaliang Formation of Tarim Basin, Datonghe Formation of Xining-Minghe basin, Jingxing Formation of Yunnan Province, Chengqiangyan Group of Sichuan province. It contains Minheella, Jingguella, Pinnocypridea, Cetacella, Prolimnocythere, Damonella ect., and has a few species of Djungarica, Ousocypris, Darwinula, Rhinocypris as well. Minheela and Jingguella are two endemic forms in the northern Tethys margin in southern China. They have a limited geographic distribution and restricted time range. Minheela and Jingguella must have a close relationship, but their convexities of posterior end of valves are different, the former is symmetrical, but the later is obviously asymmetric. Pinnocypridea has been widely recog- nized in UK, France, Germany, Spain from Portlandian (Late Jurassic) to Berriasian (Early Cretaceous), but they have been given different names, such as Cypris, Mantelliana ect., (Anderson, 1985). Cetacella can be collected from the Shushanhe Formation of Kapushaliang Group in Tarim Basin; its morphological feature is similar to the Hongshuigou Formation’s form. Although, the leading genera of this assemblage is most probably endemic, but the others are commonly appear from Late Jurassic to Early Cretaceous in Europe. Especially, Schudack (1989) argued that the genus Cetacella was found in Portlandian in Europe and Asia. We also found Cetacella in Shushanhe Formation. So, the age of this assemblage was considered to be late Tithonian of Late Jurassic to Early Cretaceous. Acknowledgements: This is a contribution to UNESCO-IUGS IGCP project 506 financially sup- ported by the Special Basic Research Program of 54 Ministry of Science and Technology of China (2006FY120300), National Natural Science Foun- dation of China (40632010) and National Committee of Stratigraphy of China. Key words: Jurassic; Ostracod assemblages; Northern China References: Anderson F.W. Ostracod faunas in the Purbeck and Wealden of England. Journal of Micropalaeon- tology, 1985, 4(2): 1-68. Anderson F.W. The Jurassic-Cretaceous transition: The nonmarine ostracod faunas. In: Casey R., Rawson P.E. (ed).The Boreal Lower Cretaceous. Liverpool: Geological Journal, Special Issue 5, 1973: 101- 110. Bate R.H. Freshwater ostracods from the Bathonian of Oxfordshire. Palaeontology, 1965, 8(4): 749-759. Deng S.H., Yao Y.M., Ye D.Q., et al. Jurassic System in the North of China (Volume I) Stratum Intro- duction. Beijing: Petroleum Industry Press, 2003: 58-65 (in Chinese). Horne D.J. A revised ostracod biostratigraphy for the Purbeck-Wealden of England. Cretaceous Re- search, 1995, 16: 636-663. Hou Y.T., Gou Y.X., Chen D.Q. Ostracods of China (Volume 1), Beijing: Science Press, 2002: 1090 (in Chinese). Jiang X.T., Zhou W.F., Lin S.P., et al. Stratigraphy and Ostracods of Xinjiang in China. Beijing: Geolo- gical Publishing House, 1995: 1-577 (in Chinese). Malz H., et al. Biostratigraphy of the Middle Jurassic of N.W. Sardinia by means of ostracods. Sencken- bergiana lethaea, 1985, 66(3-5): 299-345. Mandelyshtam M. Ostracoda from Middle Jurassic deposits Mangyshlak peninsula. Collection of articles on microfauna oilfields of the Caucasus, and central Zmby Azy. Tr. VNIGRI. S, 1947, 239-259 (in Russian). Mette W. Ostracods from the Middle Jurassic of southern Tunisia. Beringeria, Heft, Würzburg, 1995, 16: 259-348. NeutruevaI Y. Ostracods from Jurassic lacustrine deposits in Fergana and their paleobiology chara- cteristics. Science Press, 1974, 37-70 (in Russian). Schudack M.E. Neue mikropalaontoligische Beitage (Ostracoa, Charophyta) zum Morrison-Okosystem Oberjura des western Interiorn Interior, USA. Berliner geowiss. Abh., E16, Gundolf-Ernst- Festschrift, 1995: 389-407. Schudark U. Zur Systematik der oberjurassischen Ostracodengattung Cetacella Martin, 1985. (Syn. Leiria Helmdach 1971). Berliner geowiss. Abh., (A), 1989, 106: 459-471, Abb. 2, Taf.1. Ye C.H., Gou Y.X., Hou Y.T., et al. Mesozoic fossil of Yunnan (Final Volume). Beijing: Science Press, 1977: 159-160 (in Chinese).
Earth Science Frontiers, Vol. 17, Special Issue, Aug. 2010 ISSN 1005-2321 The Colorado Plateau Coring Project (CPCP): 100 Million Years of Earth System History P.E. Olsen 1* , D.V. Kent 2 , W. Geissmanjohn 3 , G. Bachmann 4 , R.C. Blakey 5 , G. Gehrels 6 , R.B. Irmis 7 , W. Kuerschner 8 , R. Molina-Garza 9 , R. Mundil 10 , J.G. Sha 11 1. Lamont-Doherty Earth Observatory of Columbia University, Palisades, New York 10964, USA 2. Earth and Planetary Sciences, Rutgers University, Piscataway, New Jersey 08854, USA 3. Department of Earth and Planetary Sciences, University of New Mexico, Albuquerque, New Mexico 87131, USA 4. Martin-Luther-Universität Halle-Wittenberg, Institut für Geowissenschaften, 06120 Halle (Saale), Germany 5. Department of Geology, Northern Arizona University, Flagstaff Arizona 86011, USA 6. Department of Geosciences, University of Arizona, Tucson, Arizona 85721, USA 7. Utah Museum of Natural History, 1390 E. Presidents Circle, Salt Lake City, Utah 84112, USA 8. Laboratory of Palaeobotany and Palynology, Utrecht University, Budapestlaan 4, 3584 CD Utrecht, Netherlands 9. Centro de Geosciencias, Campus Juriquilla UNAM, Queretaro, 76230 Mexico 10. Berkeley Geochronology Center, 2455 Ridge Rd., Berkeley, CA 94709, USA 11. Nanjing Institute of Geology and Palaeontology, Chinese Academy of Sciences, Nanjing 210008, China Lasting over 100 million years, the early Mesozoic (252 to 145 Ma) is punctuated by two of the five major mass extinctions of the Phanerozoic (Permo-Triassic and Triassic-Jurassic) plus several smaller extinction events. It witnessed the evolutionary appearance of the modern terrestrial biota including frogs, salamanders, turtles, lizards, crocodilians, dinosaurs, birds, and mammals, and spans a time of dramatic climate changes on the continents. What is arguably the richest record of these events lies in the vast (~2.5 million km 2 ) complex of epicontinental basins in the western part of Pangea, now largely preserved on the Colorado Plateau (Fig.1). Since the mid-19th century, classic studies of these basins, their strata, and their fossils have made this succession instrumental in framing our context of the early Mesozoic Earth system as reflected in the international literature. Despite this long and dis- tinguished history of study of the Colorado Plateau region, striking ambiguities in temporal resolution, major uncertainties in global correlations, and sig- nificant doubts about paleolatitudinal position hamper incorporation of the huge amount of information from the region into tests of major competing climatic, biotic, and tectonic hypotheses and a fundamental under- standing of Earth system processes. A basic question posed by the exceptionally rich paleobiological record of the Plateau and adjacent areas is, what is the nature of the links between major events in the history of early Mesozoic life, climate change, and Earth System crises, particularly the mass extinct- tion events, the ascent of the dinosaurs, and the origin of modern biota. In order to elucidate these connections we have proposed the Colorado Plateau Coring Project or CPCP (Fig.1). As proposed, the CPCP is a five-year or more, three phase interdisciplinary, multi-insti- tutional coring project designed to decipher the biotic, climatic, and tectonic evolution of the first 100 million years (Triassic and Jurassic, ~250-150 Ma) of the Mesozoic Earth System as expressed in epicontinental basins of the Colorado Plateau and its environs. The concept developed from the recommendations of a 1999 NSF-ICDP funded workshop on early Mesozoic Pangea (Olsen et al., 1999) (Western Equatorial Pangea by A. Heckert), and was more fully developed in a 2007 NSF- and DOSECC-funded workshop that provided a broad-based, community-driven science and coring plan for the CPCP. Reports of this workshop have been published in EOS (Olsen et al., 2008a), Scientific Drilling (Olsen et al., 2008b), and on the web (Olsen, 2009). An ICDP-funded international workshop was held in May 2009, in Albuquerque, NM, to refine the specific CPCP site plans and proposals (Geissman et al., 2010). These international workshops provided community-driven science and coring concepts for the CPCP. Motivating the CPCP is the need to understand the links between major events in the history of life, climate change, and Earth System crises, particularly the two major and two minor mass extinction events, the ascent of the dinosaurs, and the origin of modern biota that would be spanned by the project, and who’s fossil record is exemplary in the Colorado Plateau region. The CPCP will result in a major improvement in our ability to address out- standing issues of chronology, paleogeography, paleoclimate, and biotic evolution in the Pangea supercontinent. A scientific coring program is essential because the generally shallow bedding attitudes, lateral facies changes, and covered intervals compromise unambi- guous superposition in surface sections over long geographic traverses. This problem is exemplified by the ambiguities in compiling a composite section even across small distances in the Late Triassic Chinle Formation outcropping in Petrified Forest National Park (Martz and Parker, 2010) in the state of Arizona, the area to be cored in Phase 1 of the CPCP. Fur- thermore, the most continuous sections in outcrop are either inaccessible in vertical cliffs or are intensely weathered and geochemically altered, making geological observations and sampling at the appropriate level of detail practically impossible. Despite the seemingly 55
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